@article{weber_low_2005,
title = {Low temperature Phanerozoic history of the northern Yilgarn Craton, Western Australia.},
author = {U.D. Weber and B.P. Kohn and A.J.W. Gleadow and D.R. Nelson},
url = {http://www.geochron.com.au/wp-content/uploads/2016/11/141.-Weber-et-al-2005.pdf},
year = {2005},
date = {2005-01-01},
journal = {Tectonophysics},
volume = {400},
pages = {127--151},
abstract = {The Phanerozoic cooling history of the Western Australian Shield has been investigated using apatite fission track (AFT) thermochronology. AFT ages from the northern part of the Archaean Yilgarn Craton, Western Australia, primarily range between 200 and 280 Ma, with mean confined horizontal track lengths varying between 11.5 and 14.3 μm. Time-temperature modelling of the AFT data together with geological information suggest the onset of a regional cooling episode in the Late Carboniferous/Early Permian, which continued into Late Jurassic/Early Cretaceous time. Present-day heat flow measurements on the Western Australian Shield fall in the range of 40-50 mW m-2. If the present day geothermal gradient of ∼18 ±2 °C km-1 is representative of average Phanerozoic gradients, then this implies a minimum of ∼50 °C of Late Palaeozoic to Mesozoic cooling. Assuming that cooling resulted from denudation, the data suggest the removal of at least 3 km of rock section from the northern Yilgarn Craton over this interval. The Perth Basin, located west of the Yilgarn Craton, contains up to 15 km of mostly Permian to Lower Cretaceous clastic sediment. However, published U-Pb data of detrital zircons from Permian and Lower Triassic basin strata show relatively few or no grains of Archaean age. This suggests that the recorded cooling can probably be attributed to the removal of a sedimentary cover rather than by denudation of material from the underlying craton itself. The onset of cooling is linked to tectonism related to either the waning stages of the Alice Springs Orogeny or to the early stages of Gondwana breakup.},
keywords = {},
pubstate = {published},
tppubtype = {article}
}

The Phanerozoic cooling history of the Western Australian Shield has been investigated using apatite fission track (AFT) thermochronology. AFT ages from the northern part of the Archaean Yilgarn Craton, Western Australia, primarily range between 200 and 280 Ma, with mean confined horizontal track lengths varying between 11.5 and 14.3 μm. Time-temperature modelling of the AFT data together with geological information suggest the onset of a regional cooling episode in the Late Carboniferous/Early Permian, which continued into Late Jurassic/Early Cretaceous time. Present-day heat flow measurements on the Western Australian Shield fall in the range of 40-50 mW m-2. If the present day geothermal gradient of ∼18 ±2 °C km-1 is representative of average Phanerozoic gradients, then this implies a minimum of ∼50 °C of Late Palaeozoic to Mesozoic cooling. Assuming that cooling resulted from denudation, the data suggest the removal of at least 3 km of rock section from the northern Yilgarn Craton over this interval. The Perth Basin, located west of the Yilgarn Craton, contains up to 15 km of mostly Permian to Lower Cretaceous clastic sediment. However, published U-Pb data of detrital zircons from Permian and Lower Triassic basin strata show relatively few or no grains of Archaean age. This suggests that the recorded cooling can probably be attributed to the removal of a sedimentary cover rather than by denudation of material from the underlying craton itself. The onset of cooling is linked to tectonism related to either the waning stages of the Alice Springs Orogeny or to the early stages of Gondwana breakup.

@article{wyche_4350?3130_2004,
title = {4350-3130 Ma detrital zircons in the Southern Cross Granite-Greenstone Terrane, Western Australia: implications for the early evolution of the Yilgarn Craton.},
author = {S. Wyche and D.R. Nelson and A. Riganti},
url = {http://www.geochron.com.au/wp-content/uploads/2016/11/138.-Wyche-et-al-2004.pdf},
year = {2004},
date = {2004-01-01},
journal = {Australian Journal of Earth Sciences},
volume = {51},
pages = {31--45},
abstract = {SHRIMP U-Pb zircon analysis indicates that detrital zircons from extensive quartzite units in the Southern Cross Granite-Greenstone Terrane of the central Yilgarn Craton have ages ranging from ca 4350 Ma to ca 3130 Ma. Regional mapping studies indicate that the quartzites lie at the stratigraphic base of the exposed succession. The detrital zircon age profiles of the Southern Cross Granite-Greenstone Terrane quartzites are remarkably similar to those of quartzites in the Narryer and South West Terranes, in the northwest and southwest at the Yilgarn Craton respectively, and are significantly older than any igneous rocks that have been dated anywhere in the Yilgarn Craton other than the Narryer Terrane. Similar detrital-zircon-bearing quartzites have not been identified in the Murchison Granite-Greenstone Terrane. These age profiles suggest that the quartzites have a common depositional history. Granites in the central Yilgarn Craton are mainly younger than ca 2750 Ma and contain rare xenocrystic zircons older than 3100 Ma. If the central and western Yilgarn quartzites were all deposited at approximately the same time, the lack of preserved continental crust in the Southern Cross and Murchison Granite-Greenstone Terranes, and the South West Terrane, that is older than 3100 Ma, suggests that pre-3100 Ma Narryer-like continental crust may have been rifted or extensively reworked during deposition of greenstone successions between ca 3000 and ca 2700 Ma. If not, then a ca 4350 Ma detrital zircon in the Southern Cross Granite-Greenstone Terrane indicates more widespread, very old, continental crust than has previously been identified.},
keywords = {},
pubstate = {published},
tppubtype = {article}
}

SHRIMP U-Pb zircon analysis indicates that detrital zircons from extensive quartzite units in the Southern Cross Granite-Greenstone Terrane of the central Yilgarn Craton have ages ranging from ca 4350 Ma to ca 3130 Ma. Regional mapping studies indicate that the quartzites lie at the stratigraphic base of the exposed succession. The detrital zircon age profiles of the Southern Cross Granite-Greenstone Terrane quartzites are remarkably similar to those of quartzites in the Narryer and South West Terranes, in the northwest and southwest at the Yilgarn Craton respectively, and are significantly older than any igneous rocks that have been dated anywhere in the Yilgarn Craton other than the Narryer Terrane. Similar detrital-zircon-bearing quartzites have not been identified in the Murchison Granite-Greenstone Terrane. These age profiles suggest that the quartzites have a common depositional history. Granites in the central Yilgarn Craton are mainly younger than ca 2750 Ma and contain rare xenocrystic zircons older than 3100 Ma. If the central and western Yilgarn quartzites were all deposited at approximately the same time, the lack of preserved continental crust in the Southern Cross and Murchison Granite-Greenstone Terranes, and the South West Terrane, that is older than 3100 Ma, suggests that pre-3100 Ma Narryer-like continental crust may have been rifted or extensively reworked during deposition of greenstone successions between ca 3000 and ca 2700 Ma. If not, then a ca 4350 Ma detrital zircon in the Southern Cross Granite-Greenstone Terrane indicates more widespread, very old, continental crust than has previously been identified.

@article{occhipinti_palaeoproterozoic_2004,
title = {Palaeoproterozoic crustal accretion and collision in the southern Capricorn Orogen: the Glenburgh Orogeny},
author = {S.A. Occhipinti and S. Sheppard and C. Passchier and I.M. Tyler and D.R. Nelson},
url = {http://www.geochron.com.au/wp-content/uploads/2016/11/137.-Occhipinti-et-al-2004.pdf},
year = {2004},
date = {2004-01-01},
journal = {Precambrian Research},
volume = {128},
pages = {237--255},
abstract = {The Capricorn Orogen in central Western Australia records the Palaeoproterozoic collision of the Archaean Pilbara and Yilgarn Cratons. Until recently only one orogenic event was thought to be the cause of this collision, the 1830-1780Ma Capricorn Orogeny. However, recent work has uncovered an older event, the Glenburgh Orogeny that occurred between 2000 and 1960Ma. The Glenburgh Orogeny reflects the collision of a late Archaean to Palaeoproterozoic microcontinent (the Glenburgh Terrane) with the Archaean Yilgarn Craton and is therefore tectonically distinct as well as significantly older than the widespread 1900-1800Ma tectonothermal events recorded in northern Australia. The Glenburgh Terrane preserves a different history from either the Yilgarn or Pilbara Cratons. Granitic gneiss protoliths dated at ca. 2550Ma were intruded by widespread granite magmatism dated at 2005-1970Ma, accompanied by high-grade metamorphism and deformation throughout the terrane. At ca. 1960Ma silicic granite of the Bertibubba Supersuite intruded the northern margin of the Yilgarn Craton along the Errabiddy Shear Zone, a crustal-scale shear zone that today marks the contact of the Glenburgh Terrane and Yilgarn Craton. At ca. 1950Ma silicic dykes intruded the southernmost part of the Glenburgh Terrane, marking the end of the Glenburgh Orogeny. East of the Glenburgh Terrane the Glenburgh Orogeny resulted in the cessation of mafic volcanism in the Bryah Basin, and the basin's eventual closure. Siliciclastic, carbonate and chemical sedimentary rocks were deposited in the Padbury Basin that formed a retro-arc foreland basin on top of the Bryah Basin, and probably records the later stages of the Glenburgh Orogeny collision.},
keywords = {},
pubstate = {published},
tppubtype = {article}
}

The Capricorn Orogen in central Western Australia records the Palaeoproterozoic collision of the Archaean Pilbara and Yilgarn Cratons. Until recently only one orogenic event was thought to be the cause of this collision, the 1830-1780Ma Capricorn Orogeny. However, recent work has uncovered an older event, the Glenburgh Orogeny that occurred between 2000 and 1960Ma. The Glenburgh Orogeny reflects the collision of a late Archaean to Palaeoproterozoic microcontinent (the Glenburgh Terrane) with the Archaean Yilgarn Craton and is therefore tectonically distinct as well as significantly older than the widespread 1900-1800Ma tectonothermal events recorded in northern Australia. The Glenburgh Terrane preserves a different history from either the Yilgarn or Pilbara Cratons. Granitic gneiss protoliths dated at ca. 2550Ma were intruded by widespread granite magmatism dated at 2005-1970Ma, accompanied by high-grade metamorphism and deformation throughout the terrane. At ca. 1960Ma silicic granite of the Bertibubba Supersuite intruded the northern margin of the Yilgarn Craton along the Errabiddy Shear Zone, a crustal-scale shear zone that today marks the contact of the Glenburgh Terrane and Yilgarn Craton. At ca. 1950Ma silicic dykes intruded the southernmost part of the Glenburgh Terrane, marking the end of the Glenburgh Orogeny. East of the Glenburgh Terrane the Glenburgh Orogeny resulted in the cessation of mafic volcanism in the Bryah Basin, and the basin's eventual closure. Siliciclastic, carbonate and chemical sedimentary rocks were deposited in the Padbury Basin that formed a retro-arc foreland basin on top of the Bryah Basin, and probably records the later stages of the Glenburgh Orogeny collision.

@article{trendall_shrimp_2004,
title = {SHRIMP zircon ages constraining on the depositional chronology of the Hamersley Group, Western Australia.},
author = {A.F. Trendall and W. Compston and D.R. Nelson and J.R. de Laeter and V.C. Bennett},
url = {http://www.geochron.com.au/wp-content/uploads/2016/11/136.-Trendall-et-al-2004.pdf},
year = {2004},
date = {2004-01-01},
journal = {Australian Journal of Earth Sciences},
volume = {51},
pages = {621--644},
abstract = {The Mt Bruce Supergroup of Western Australia was laid down between ca 2.8 Ga and ca 2.2 Ga in the Hamersley Basin, unconformably over a basement of the older, granite-greenstone, component of the Pilbara Craton. The Mt Bruce Supergroup consists of three groups: the Fortescue Group, Hamersley Group and Turee Creek Group in upward sequence. The Hamersley Group, which is divided into eight formations, has a general thickness of ∼2.5 km, and is characterised by major banded iron-formation (BIF) units. Reported here are SHRIMP U-Pb zircon results (406 grain analyses) from 13 samples taken from the Hamersley Group and near the top of the underlying Fortescue Group. In combination with SHRIMP results previously published from 12 Hamersley Group samples, the present results provide significant new constraints on the depositional chronology of the group, and suggest that the average (compacted) depositional rates of each of the main depositional lithologies (BIF, carbonate, shale) were ∼180 m per million years, 12 m per million years and 5 m per million years, respectively. Some recently published SHRIMP ages from the Joffre Member differ slightly from those that are interpreted from the present data, and it is suggested that the two datasets may be reconciled if non-zero-age Pb loss is taken into account. The total body of zircon U-Pb age data from the Fortescue and Hamersley Groups is consistent with a model involving continuous accumulation of basin-fill for at least 330 million years, from ca 2780 Ma to the top of the Hamersley Group at ca 2449 Ma. The word 'continuous' in this context means that there may have been no breaks in deposition longer than 1 million years. However, this model is not proven, and a major challenge for future work is to measure the length of any proposed non-depositional intervals.},
keywords = {},
pubstate = {published},
tppubtype = {article}
}

The Mt Bruce Supergroup of Western Australia was laid down between ca 2.8 Ga and ca 2.2 Ga in the Hamersley Basin, unconformably over a basement of the older, granite-greenstone, component of the Pilbara Craton. The Mt Bruce Supergroup consists of three groups: the Fortescue Group, Hamersley Group and Turee Creek Group in upward sequence. The Hamersley Group, which is divided into eight formations, has a general thickness of ∼2.5 km, and is characterised by major banded iron-formation (BIF) units. Reported here are SHRIMP U-Pb zircon results (406 grain analyses) from 13 samples taken from the Hamersley Group and near the top of the underlying Fortescue Group. In combination with SHRIMP results previously published from 12 Hamersley Group samples, the present results provide significant new constraints on the depositional chronology of the group, and suggest that the average (compacted) depositional rates of each of the main depositional lithologies (BIF, carbonate, shale) were ∼180 m per million years, 12 m per million years and 5 m per million years, respectively. Some recently published SHRIMP ages from the Joffre Member differ slightly from those that are interpreted from the present data, and it is suggested that the two datasets may be reconciled if non-zero-age Pb loss is taken into account. The total body of zircon U-Pb age data from the Fortescue and Hamersley Groups is consistent with a model involving continuous accumulation of basin-fill for at least 330 million years, from ca 2780 Ma to the top of the Hamersley Group at ca 2449 Ma. The word 'continuous' in this context means that there may have been no breaks in deposition longer than 1 million years. However, this model is not proven, and a major challenge for future work is to measure the length of any proposed non-depositional intervals.

Lithostratigraphy of the Late Archaean Marda-Diemals greenstone belt in the Southern Cross Terrane, central Yilgarn Craton defines a temporal change from mafic volcanism to felsic-intermediate volcanism to clastic sedimentation. A ca. 3.0 Ga lower greenstone succession is characterised by mafic volcanic rocks and banded iron-formation (BIF). It is subdivided into three lithostratigraphic associations and unconformably overlain by the ca. 2.73 Ga upper greenstone succession of calc-alkaline volcanic (Marda Complex) and clastic sedimentary rocks (Diemals Formation). D1 north-south, low-angle thrusting was restricted to the lower greenstone succession and preceded deposition of the upper greenstone succession. D2 east-west, orogenic compression ca. 2730-2680 Ma occurred in two stages; an earlier folding phase and a late phase that resulted in deposition and deformation of the Diemals Formation. Progressive and inhomogeneous east-west shortening ca. 2680-2655 Ma (D3) produced regional-scale shear zones and arcuate structures. The lithostratigraphy and tectonic history of the Marda-Diemals greenstone belt are broadly similar to the northern Murchison Terrane in the western Yilgarn Craton, but has older greenstones and deformation events than the southern Eastern Goldfields Terrane of the eastern Yilgarn Craton. This indicates that the Eastern Goldfields Terrane may have accreted to an older Murchison-Southern Cross granite-greenstone nucleus.

@article{beintema_new_2003,
title = {New constraints of the timing of tectonic activity in the Archaean Central Pilbara Craton, Western Australia. In: M.A. Forster and J.R. Wijbrans (Editors), Geochronology and Structural Geology.},
author = {K.A. Beintema and P.R.D. Mason and D.R. Nelson and S.H. White and J.R. Wijbrans},
url = {http://www.geochron.com.au/wp-content/uploads/2016/11/119.-Bientema-et-al-2003.pdf},
year = {2003},
date = {2003-01-01},
journal = {Journal of the Virtual Explorer},
volume = {13},
pages = {1--42},
abstract = {The Archaean Pilbara Craton in Western Australia has a domainal architecture which has been interpreted to reflect a history of accretion. The Tabba Tabba Shear Zone is the major division between the East and West Pilbara blocks: this interpretation is based on significant differences in the tectono-thermal histories of the bordering terranes. New laser ablation ICP-MS and SHRIMP U-Pb zircon geochronological data, coupled with trace element data for the same core parts of the sampled mineral grains, indicate a range of magmatic crystallization ages for representative igneous rocks emplaced before, during or after shearing. Results from both dating techniques agree for two separate homogeneous samples to within analytical error (2s). Our data indicate that a granodioritic suite intruded the area at about 3250 Ma, followed by gabbroic suite at 3235 Ma. The area was subsequently affected by an early dextral compressive event during which the Tabba Tabba Shear Zone was formed, and the granodiorites and gabbros were incorporated into the Tabba Tabba Shear Zone. A granitoid suite intruded the shear zone at 2940 Ma, with xenocrystic populations of 3115 Ma and 3015 Ma, a possibly West Pilbara association. The East and West Pilbara terranes may thus have been relatively close to each other between 3250 and 3115 Ma. The Tabba Tabba Shear Zone currently forms the eastern bounding fault of the Mallina Basin. The last major activity in the structure occurred during a major phase of oblique movement, corresponding to closure of the Mallina Basin. Ages of late syn-kinematic granitic intrusions indicate that this occurred at about 2940 Ma.},
keywords = {},
pubstate = {published},
tppubtype = {article}
}

The Archaean Pilbara Craton in Western Australia has a domainal architecture which has been interpreted to reflect a history of accretion. The Tabba Tabba Shear Zone is the major division between the East and West Pilbara blocks: this interpretation is based on significant differences in the tectono-thermal histories of the bordering terranes. New laser ablation ICP-MS and SHRIMP U-Pb zircon geochronological data, coupled with trace element data for the same core parts of the sampled mineral grains, indicate a range of magmatic crystallization ages for representative igneous rocks emplaced before, during or after shearing. Results from both dating techniques agree for two separate homogeneous samples to within analytical error (2s). Our data indicate that a granodioritic suite intruded the area at about 3250 Ma, followed by gabbroic suite at 3235 Ma. The area was subsequently affected by an early dextral compressive event during which the Tabba Tabba Shear Zone was formed, and the granodiorites and gabbros were incorporated into the Tabba Tabba Shear Zone. A granitoid suite intruded the shear zone at 2940 Ma, with xenocrystic populations of 3115 Ma and 3015 Ma, a possibly West Pilbara association. The East and West Pilbara terranes may thus have been relatively close to each other between 3250 and 3115 Ma. The Tabba Tabba Shear Zone currently forms the eastern bounding fault of the Mallina Basin. The last major activity in the structure occurred during a major phase of oblique movement, corresponding to closure of the Mallina Basin. Ages of late syn-kinematic granitic intrusions indicate that this occurred at about 2940 Ma.

@article{van_kranendonk_geology_2002,
title = {Geology and tectonic evolution of the Archaean North Pilbara Terrain, Pilbara Craton, Western Australia.},
author = {M.J. Van Kranendonk and A.H. Hickman and R.H. Smithies and D.R. Nelson and G. Pike},
url = {http://www.geochron.com.au/wp-content/uploads/2016/11/110.-VanKran-et-al.pdf},
year = {2002},
date = {2002-01-01},
journal = {Economic Geology},
volume = {97},
pages = {695--732},
abstract = {Results from a multidisciplinary geoscience program since 1994 are summarized for the North Pilbara terrain of the Pilbara Craton. Major findings include the recognition of three separate terranes with unique stratigraphy, geochronological, and structural histories; the ca. 3.72 to 2.85 Ga East Pilbara granite- greenstone terrane, the ca. 3.27 to 2.92 Ga West Pilbara granite-greenstone terrane, and the ≤3.29 Ga Kuranna terrane in the southeast. These are separated by two late, dominantly elastic sedimentary basins deposited within tectonically active zones; the ca. 3.01 to 2.93 Ga Mallina basin in the west and the undated Mosquito Creek basin in the east. The oldest supracrustal rocks are the ca. 3.51 to 3.50 Ga Coonterunah and ca. 3.49 to 3.31 Ga Warrawoona Groups in the East Pilbara granite-greenstone terrane, deposited on fragments of older sialic crust to 3.72 Ga. The Warrawoona Group is subdivided into three main (ultra)mafic-felsic volcanic cycles including from base to top, the Talga (3.49-3.46 Ga), Salgasli (3.46-3.43 Ga), and newly defined Kelly (3.43-3.31 Ga) Sub- groups. These dominantly basaltic rocks include chert beds containing Earth's oldest stromatolites and are interbedded with significant felsic volcanics erupted intermittently from 3.49 to 3.43 Ga during emplacement of sheeted sodic granitoid sills. Estimates of autochthonous stratigraphic thickness range from 9 to 18 km. Deformation involved extensional growth faulting, local folding, and tilting of greenstones away from synvolcanic granitoid domes. Rapid partial convective overturn of upper and middle crust occurred at 3.32 Ga during voluminous potassic felsic magmatism, followed by deposition of the Budjan Creek Formation at 3.31 Ga. Granitoid plutonism at ca. 3.29 Ga in the Kuranna terrane preceded deposition of ultramafic through felsic volcanics and chert in the West Pilbara granite-greenstone terrane (3.27-3.25 Ga Roebourne Group) and western margin of the East Pilbara granite-greenstone terrane (3.26-3.24 Ga Sulphur Springs Group). Geochemical and isotopic data suggest that volcanism resulted from plume-related rifting of the East Pilbara granite-greenstone terrane, which was accompanied by granitoid plutonism and deformation. Following this was ca. 100 m.y. of relative quiescence during which locally economic concentrations of banded iron-formation and siliciclastics of the Gorge Creek Group were deposited in the East Pilbara granite-greenstone terrane. Thereafter, geologic events are more consistent with microplate tectonics, commencing with deformation at 3.15 Ga followed by deposition of 3.13 to 3.11 Ga bimodal volcanics in the West Pilbara granite-greenstone terrane (Whundo Group), which have juvenile Nd isotope signatures and thus may represent either a rift or island- are succession. Basaltic rocks and minor felsic tuff were deposited in the East Pilbara granite-greenstone terrane at 3.06 Ga and possibly in the West Pilbara granite-greenstone terrane (Regal Formation). At 3.02 Ga. the Whundo and Roebourne Groups share a common history of deposition of banded iron-formation and granitoid plutonism across the Sholl shear zone, suggesting accretion at, or immediately preceding, this time. This was followed by deposition in the Mallina basin of the volcanic Whim Creek Group at 3.01 Ga, possibly as an arc, and then the 2.97 to 2.93 Ga volcanic Bookingarra (west) and clastic De Grey (east) Groups during periods of intracontinental rifting interspersed with compression and granitoid intrusion. The geochemistry of 2.95 Ga high Mg diorites (sanukitoids) indicates a previous episode of subduction during either the Whundo or Whim Creek Groups or both. Final events include emplacement of ultramafic-mafic layered intrusions (2.925 Ga in the West Pilbara granite-greenstone terrane), local shearing and lode Au mineralization (2.92 Ga in the West Pilbara granite-greenstone terrane, 2.90 Ga in the Mosquito Creek basin, 2.89 Ga in the East Pilbara granite-greenstone terrane), and intrusion of fractionated, Sn-Ta-Li-bearing granites to 2.85 Ga (East Pilbara granite-greenstone terrane).},
keywords = {},
pubstate = {published},
tppubtype = {article}
}

Results from a multidisciplinary geoscience program since 1994 are summarized for the North Pilbara terrain of the Pilbara Craton. Major findings include the recognition of three separate terranes with unique stratigraphy, geochronological, and structural histories; the ca. 3.72 to 2.85 Ga East Pilbara granite- greenstone terrane, the ca. 3.27 to 2.92 Ga West Pilbara granite-greenstone terrane, and the ≤3.29 Ga Kuranna terrane in the southeast. These are separated by two late, dominantly elastic sedimentary basins deposited within tectonically active zones; the ca. 3.01 to 2.93 Ga Mallina basin in the west and the undated Mosquito Creek basin in the east. The oldest supracrustal rocks are the ca. 3.51 to 3.50 Ga Coonterunah and ca. 3.49 to 3.31 Ga Warrawoona Groups in the East Pilbara granite-greenstone terrane, deposited on fragments of older sialic crust to 3.72 Ga. The Warrawoona Group is subdivided into three main (ultra)mafic-felsic volcanic cycles including from base to top, the Talga (3.49-3.46 Ga), Salgasli (3.46-3.43 Ga), and newly defined Kelly (3.43-3.31 Ga) Sub- groups. These dominantly basaltic rocks include chert beds containing Earth's oldest stromatolites and are interbedded with significant felsic volcanics erupted intermittently from 3.49 to 3.43 Ga during emplacement of sheeted sodic granitoid sills. Estimates of autochthonous stratigraphic thickness range from 9 to 18 km. Deformation involved extensional growth faulting, local folding, and tilting of greenstones away from synvolcanic granitoid domes. Rapid partial convective overturn of upper and middle crust occurred at 3.32 Ga during voluminous potassic felsic magmatism, followed by deposition of the Budjan Creek Formation at 3.31 Ga. Granitoid plutonism at ca. 3.29 Ga in the Kuranna terrane preceded deposition of ultramafic through felsic volcanics and chert in the West Pilbara granite-greenstone terrane (3.27-3.25 Ga Roebourne Group) and western margin of the East Pilbara granite-greenstone terrane (3.26-3.24 Ga Sulphur Springs Group). Geochemical and isotopic data suggest that volcanism resulted from plume-related rifting of the East Pilbara granite-greenstone terrane, which was accompanied by granitoid plutonism and deformation. Following this was ca. 100 m.y. of relative quiescence during which locally economic concentrations of banded iron-formation and siliciclastics of the Gorge Creek Group were deposited in the East Pilbara granite-greenstone terrane. Thereafter, geologic events are more consistent with microplate tectonics, commencing with deformation at 3.15 Ga followed by deposition of 3.13 to 3.11 Ga bimodal volcanics in the West Pilbara granite-greenstone terrane (Whundo Group), which have juvenile Nd isotope signatures and thus may represent either a rift or island- are succession. Basaltic rocks and minor felsic tuff were deposited in the East Pilbara granite-greenstone terrane at 3.06 Ga and possibly in the West Pilbara granite-greenstone terrane (Regal Formation). At 3.02 Ga. the Whundo and Roebourne Groups share a common history of deposition of banded iron-formation and granitoid plutonism across the Sholl shear zone, suggesting accretion at, or immediately preceding, this time. This was followed by deposition in the Mallina basin of the volcanic Whim Creek Group at 3.01 Ga, possibly as an arc, and then the 2.97 to 2.93 Ga volcanic Bookingarra (west) and clastic De Grey (east) Groups during periods of intracontinental rifting interspersed with compression and granitoid intrusion. The geochemistry of 2.95 Ga high Mg diorites (sanukitoids) indicates a previous episode of subduction during either the Whundo or Whim Creek Groups or both. Final events include emplacement of ultramafic-mafic layered intrusions (2.925 Ga in the West Pilbara granite-greenstone terrane), local shearing and lode Au mineralization (2.92 Ga in the West Pilbara granite-greenstone terrane, 2.90 Ga in the Mosquito Creek basin, 2.89 Ga in the East Pilbara granite-greenstone terrane), and intrusion of fractionated, Sn-Ta-Li-bearing granites to 2.85 Ga (East Pilbara granite-greenstone terrane).

@article{eriksson_late_2002,
title = {Late Archaean superplume events: a Kaapvaal-Pilbara perspective.},
author = {P.G. Eriksson and K.C. Condie and W. van der Westhuizen and R. van der Merwe and H. de Bruiyn and D.R. Nelson and W. Altermann and O. Catuneanu and A.J. Bumby and J. Lindsay and M.J. Cunningham},
url = {http://www.geochron.com.au/wp-content/uploads/2016/11/112.-Eriksson-et-al-2002.pdf},
year = {2002},
date = {2002-01-01},
journal = {Journal of Geodynamics},
volume = {34},
pages = {207--247},
abstract = {The 2714-2709 Ma Ventersdorp Supergroup overlies Mesoarchaen basement rocks and sedimentary strata of the Neoarchaean Witwatersrand Supergroup. The latter basin was inverted by tectonic shortening and suffered the loss of up to 1.5 km of stratigraphy prior to deposition of the Ventersdorp volcanics. Thermal uplift and fluvial incision prior to the basal Klipriviersberg Group flood basalts appear to have been limited, but this could also reflect a hot dry palaeoclimate acting on a peneplained plateau. Rapid ascent of ponded magma beneath thinned sub-Witwaterstrand lithosphere, transported laterally from a mantle plume starting head possibly situated marginally to the Kaapvaal craton is inferred for this unit of up to 2 km of predominantly tholeiitic basalts with subordinate, basal komatiites. Crustal extension related to ascent of the ponded magma followed, leading to the formation of a set of graben and half-graben basins, in which immature clastic sedimentary, and felsic to mafic lavas and pyroclastics of the Platberg Group were laid down. The Platberg basins show no evidence for reactivation of pre-existing crustal structures. The Fortescue Group of the Pilbara craton has an analogous lower flood basaltic succession, followed by graben-fills similar to those of the Platberg Group. Differences in the Fortescue include evidence for significant thermal uplift prior to the onset of volcanism, subaqueous basalts in the south of the Pilbara craton, evidence for two episodes of flood basaltic volcanism, possibly related to two plumes at c. 2765 and 2715 Ma, and graben basins aligned along existing cratonic structures. Both Kaapvaal and Pilbara flood basalts and graben-related sedimentary- volcanic deposits are thought to have been part of a c. 2.7 Ga global superplume event. The plume inferred for the Fortescue Group flood basalts was probably related to rifting and the breakup of a plate larger than the preserved Pilbara craton. Uppermost Ventersdorp units (Bothaville Formation terrestrial clastic and Allanridge Formation tholeiitic rocks) suggest a combination of thermal subsidence, allied to continued plume (minor komatiites) and graben basin influences. In the Kaapvaal craton, the Transvaal Supergroup lies unconformably above the Ventersdorp. Basal "protobasinal" successions reflect discrete fault-bounded basin-fills, analogous to those of the Platberg Group; however, it is inferred that the former depositories were related to craton marginal plate tectonic influences, specifically the c. 2.6 Ga Limpopo orogeny. Thin fluvial sheet sandstones of the Black Reef Formation unconformably succeed the protobasinal rocks and reflect the transition to an epeiric drowning of much of the Kaapvaal craton. A shallow shelf carbonate-banded iron formation platform succession (Chuniespoort-Ghaap Groups) developed in two sub-basins on the Kaapvaal craton. They are mirrored by the approximately coeval Hamersley chemical epeiric sediments on the Pilbara craton, and both Kaapvaal and Pilbara transgressive successions are related here to a possible second, c. 2.5 Ga superplume event, which raised sea levels globally. Evidence for the younger superplume event is less clear than for the c. 2.7 Ga event.},
keywords = {},
pubstate = {published},
tppubtype = {article}
}

The 2714-2709 Ma Ventersdorp Supergroup overlies Mesoarchaen basement rocks and sedimentary strata of the Neoarchaean Witwatersrand Supergroup. The latter basin was inverted by tectonic shortening and suffered the loss of up to 1.5 km of stratigraphy prior to deposition of the Ventersdorp volcanics. Thermal uplift and fluvial incision prior to the basal Klipriviersberg Group flood basalts appear to have been limited, but this could also reflect a hot dry palaeoclimate acting on a peneplained plateau. Rapid ascent of ponded magma beneath thinned sub-Witwaterstrand lithosphere, transported laterally from a mantle plume starting head possibly situated marginally to the Kaapvaal craton is inferred for this unit of up to 2 km of predominantly tholeiitic basalts with subordinate, basal komatiites. Crustal extension related to ascent of the ponded magma followed, leading to the formation of a set of graben and half-graben basins, in which immature clastic sedimentary, and felsic to mafic lavas and pyroclastics of the Platberg Group were laid down. The Platberg basins show no evidence for reactivation of pre-existing crustal structures. The Fortescue Group of the Pilbara craton has an analogous lower flood basaltic succession, followed by graben-fills similar to those of the Platberg Group. Differences in the Fortescue include evidence for significant thermal uplift prior to the onset of volcanism, subaqueous basalts in the south of the Pilbara craton, evidence for two episodes of flood basaltic volcanism, possibly related to two plumes at c. 2765 and 2715 Ma, and graben basins aligned along existing cratonic structures. Both Kaapvaal and Pilbara flood basalts and graben-related sedimentary- volcanic deposits are thought to have been part of a c. 2.7 Ga global superplume event. The plume inferred for the Fortescue Group flood basalts was probably related to rifting and the breakup of a plate larger than the preserved Pilbara craton. Uppermost Ventersdorp units (Bothaville Formation terrestrial clastic and Allanridge Formation tholeiitic rocks) suggest a combination of thermal subsidence, allied to continued plume (minor komatiites) and graben basin influences. In the Kaapvaal craton, the Transvaal Supergroup lies unconformably above the Ventersdorp. Basal "protobasinal" successions reflect discrete fault-bounded basin-fills, analogous to those of the Platberg Group; however, it is inferred that the former depositories were related to craton marginal plate tectonic influences, specifically the c. 2.6 Ga Limpopo orogeny. Thin fluvial sheet sandstones of the Black Reef Formation unconformably succeed the protobasinal rocks and reflect the transition to an epeiric drowning of much of the Kaapvaal craton. A shallow shelf carbonate-banded iron formation platform succession (Chuniespoort-Ghaap Groups) developed in two sub-basins on the Kaapvaal craton. They are mirrored by the approximately coeval Hamersley chemical epeiric sediments on the Pilbara craton, and both Kaapvaal and Pilbara transgressive successions are related here to a possible second, c. 2.5 Ga superplume event, which raised sea levels globally. Evidence for the younger superplume event is less clear than for the c. 2.7 Ga event.

@article{anderson_lead_2002,
title = {Lead isotope evolution of the mineral deposits in the Proterozoic Throssell Group, Western Australia.},
author = {B.R. Anderson and J.B. Gemmell and D.R. Nelson},
url = {http://www.geochron.com.au/wp-content/uploads/2016/11/111.-Andersen-et-al-2002.pdf},
year = {2002},
date = {2002-01-01},
journal = {Economic Geology},
volume = {97},
pages = {897--911},
abstract = {The Meso-Neoproterozoic Throssell Group of the Paterson orogen in Western Australia hosts the Nifty and Maroochydore sediment-hosted, replacement Cu deposits, as well as subeconomic Pb-Cu-Au veins at Goosewacker, carbonate-hosted Zn-Pb at Warrabarty, and pyritic massive sulfide at Grevillea. We report new Pb isotope data for the Nifty deposit and the Rainbow and Grevillea prospects. These data are combined with published and unpublished data to characterize the Pb isotope signatures of the deposits and prospects in the Throssell Group. In addition these data are integrated into a model for the sources of Pb in the mineralizing systems. Lead isotope data from mineralized occurrences in the Throssell Group plot as a linear trend in 207Pb/ 204Pb- 206Pb/ 204Pb space. Deposits and prospects are arranged, from least to most radiogenic, as Rainbow, Warrabarty, Nifty, Goosewacker, and Maroochydore, along the trend. Secondary isochron or mixing isochron models were previously proposed to interpret the Pb isotope trend for mineral deposits and prospects in the Throssell Group. Our investigation shows that the linear trend does not represent an isochron due to the syngenetic (pre- D 4) timing for mineralization at Warrabarty and Rainbow compared to an epigenetic (syn-D 4) timing for Maroochydore, Nifty, and Goosewacker. We propose a source-mixing model, with no time dependency, to explain the deposit Pb isotope linear trend where Pb from a primitive, mantle source (Pilbara Craton, μ = 9.88) is mixed with crustal Pb (Throssell Group sedimentary rock derived from the Rudall Complex, μ = 10.55). The position of deposits and prospects along the trend suggests that the Warrabarty and Rainbow prospects have more primitive Pb and that the Maroochydore deposit contains Pb from primarily a crustal source. The Nifty deposit, and the Goosewacker and Grevillea prospects, contain a mixture of both primitive and crustal Pb.},
keywords = {},
pubstate = {published},
tppubtype = {article}
}

The Meso-Neoproterozoic Throssell Group of the Paterson orogen in Western Australia hosts the Nifty and Maroochydore sediment-hosted, replacement Cu deposits, as well as subeconomic Pb-Cu-Au veins at Goosewacker, carbonate-hosted Zn-Pb at Warrabarty, and pyritic massive sulfide at Grevillea. We report new Pb isotope data for the Nifty deposit and the Rainbow and Grevillea prospects. These data are combined with published and unpublished data to characterize the Pb isotope signatures of the deposits and prospects in the Throssell Group. In addition these data are integrated into a model for the sources of Pb in the mineralizing systems. Lead isotope data from mineralized occurrences in the Throssell Group plot as a linear trend in 207Pb/ 204Pb- 206Pb/ 204Pb space. Deposits and prospects are arranged, from least to most radiogenic, as Rainbow, Warrabarty, Nifty, Goosewacker, and Maroochydore, along the trend. Secondary isochron or mixing isochron models were previously proposed to interpret the Pb isotope trend for mineral deposits and prospects in the Throssell Group. Our investigation shows that the linear trend does not represent an isochron due to the syngenetic (pre- D 4) timing for mineralization at Warrabarty and Rainbow compared to an epigenetic (syn-D 4) timing for Maroochydore, Nifty, and Goosewacker. We propose a source-mixing model, with no time dependency, to explain the deposit Pb isotope linear trend where Pb from a primitive, mantle source (Pilbara Craton, μ = 9.88) is mixed with crustal Pb (Throssell Group sedimentary rock derived from the Rudall Complex, μ = 10.55). The position of deposits and prospects along the trend suggests that the Warrabarty and Rainbow prospects have more primitive Pb and that the Maroochydore deposit contains Pb from primarily a crustal source. The Nifty deposit, and the Goosewacker and Grevillea prospects, contain a mixture of both primitive and crustal Pb.

@article{nelson_assessment_2001,
title = {An assessment of the determination of depositional ages for Precambrian clastic sedimentary rocks by U-Pb dating of detrital zircons.},
author = {D.R. Nelson},
url = {http://www.geochron.com.au/wp-content/uploads/2016/11/97.-Nelson-2001.pdf},
year = {2001},
date = {2001-01-01},
journal = {Sedimentary Geology},
volume = {141-142},
pages = {37--60},
abstract = {Methodologies for the determination of depositional ages for clastic sedimentary rocks by ion microprobe U-Pb analysis of their detrital zircon populations are described. Provided there has been no sample contamination or disturbance of the U-Pb system, the youngest igneous crystallization dates obtained on detrital zircons from a sedimentary rock sample will provide a maximum age for sediment deposition. Maximum depositional ages so obtained are comparable to minimum ages determined from the dating of cross-cutting dykes, or of metamorphic or diagenetic minerals, but a significant advantage of this approach is that detrital zircons are virtually ubiquitous in clastic sedimentary rocks. The advantages and limitations of this approach are demonstrated in case studies of sedimentary rocks from the Archaean Yilgarn Craton, the Mesoproterozoic Albany-Fraser Orogen and the Neoproterozoic Officer Basin of Australia. These examples demonstrate that the probability that maximum deposition ages based on the dating of detrital zircons are close to the time of sediment deposition is influenced by the lithological characteristics of the sediment samples, with the best results obtained from lithologies with the widest possible provenance range represented in their detrital zircon populations. Due to difficulties in matching wide provenance ranges to particular source areas, lithologies that are suited to maximum depositional age determinations are not necessarily suited to provenance studies. The approach will find applications particularly in studies of sedimentary basins that lack volcanic or intrusive rocks amenable to radiometric dating.},
keywords = {},
pubstate = {published},
tppubtype = {article}
}

Methodologies for the determination of depositional ages for clastic sedimentary rocks by ion microprobe U-Pb analysis of their detrital zircon populations are described. Provided there has been no sample contamination or disturbance of the U-Pb system, the youngest igneous crystallization dates obtained on detrital zircons from a sedimentary rock sample will provide a maximum age for sediment deposition. Maximum depositional ages so obtained are comparable to minimum ages determined from the dating of cross-cutting dykes, or of metamorphic or diagenetic minerals, but a significant advantage of this approach is that detrital zircons are virtually ubiquitous in clastic sedimentary rocks. The advantages and limitations of this approach are demonstrated in case studies of sedimentary rocks from the Archaean Yilgarn Craton, the Mesoproterozoic Albany-Fraser Orogen and the Neoproterozoic Officer Basin of Australia. These examples demonstrate that the probability that maximum deposition ages based on the dating of detrital zircons are close to the time of sediment deposition is influenced by the lithological characteristics of the sediment samples, with the best results obtained from lithologies with the widest possible provenance range represented in their detrital zircon populations. Due to difficulties in matching wide provenance ranges to particular source areas, lithologies that are suited to maximum depositional age determinations are not necessarily suited to provenance studies. The approach will find applications particularly in studies of sedimentary basins that lack volcanic or intrusive rocks amenable to radiometric dating.

@article{eriksson_introduction_2001,
title = {An introduction to Precambrian basins: their characteristics and genesis.},
author = {P.G. Eriksson and M.A. Martins-Neto and D.R. Nelson and L.B. Aspler and J.R. Chiarenzelli and O. Catuneanu and S. Sarkar and W. Altermann and C.J. de W. Rautenbach},
url = {http://www.geochron.com.au/wp-content/uploads/2016/11/96.-Eriksson-et-al-2001.pdf},
year = {2001},
date = {2001-01-01},
journal = {Sedimentary Geology},
volume = {141-142},
pages = {1--35},
abstract = {Precambrian and younger basins reflect the interaction of sediment supply and subsidence; the latter is generally ascribed to tectonic, magmatic and related thermal processes. The interplay of supply and subsidence is further modified by eustasy and palaeoclimate. Problems and enigmas inherent in analysis of Precambrian basin-fills include: a spectrum of ideas on the maximum age of Phanerozoic-style plate tectonics in the rock record; Archaean heat flow up to two to three times present values; changes in magmatism over time (including global magmatic events); the evolution of atmospheric composition and of life and their influence on weathering, erosion and sediment supply rates; degree of preservation, deformation and metamorphism, and preservational bias (especially of intracratonic basins which would lack evidence for early plate tectonics); a limited rock record; poor age constraints, inherent errors in geochronological techniques and difficulty in dating the time of deposition of sedimentary rocks. Major influences on Precambrian basin formation are assumed to include magmatism, plate tectonics, eustasy and palaeoclimate, all of which interacted. Models for greenstone belt evolution include plate tectonic intra-oceanic generation, plume-generated oceanic plateau, and global catastrophic magmatic events that may have been transitional to a plate tectonic regime over several hundred million years. The latter transition may have included the onset of the supercontinent cycle. Insignificant preservation of Precambrian ocean floor makes evaluation of these models problematic. Eustasy was intrinsically related to continental crustal growth rates, continental freeboard and the hypsometric curves of emerging cratons. Possible maximum crustal growth rates near the Archaean-Proterozoic boundary led to globally elevated sea levels, and the formation of enormous carbonate-banded iron formation platforms where cyanobacterial mats, which produced oxygen, flourished. The combination of changes in cratonic growth rates, thermal elevation of cratons, eustasy, weathering and palaeo-atmosphere composition may have combined to produce the first global glaciation at ca. 2.4-2.2 Ga. Examples of basins discussed here emphasise the interaction of tectonism, magmatism, eustasy and palaeoclimate in their evolution. For the Neoarchaean Witwatersrand basin (Kaapvaal craton, South Africa), evidence for all these factors is preserved in the basin-fill, whereas for the Neoproterozoic Macaúbas basin (São Francisco craton, Brazil), clear evidence for eustasy is more limited. The ca. <2.45-<1.9 Ga preserved Hurwitz basin (Hearne domain, Canada) suggests a predominant tectonic control, but with significant influences from magmatic processes, eustasy and palaeoclimate. For the ca. 2.7 Ga Ventersdorp Supergroup, which succeeded the Witwatersrand Supergroup, a strong case can be made for magmatism as a prime influence, with an inferred mantle plume having caused lithospheric stretching and thermal subsidence. The Ventersdorp formed part of an inferred global magmatic event, succeeded on the Pilbara and Kaapvaal cratons by the NeoArchaean-Palaeoproterozoic Hamersley and Lower Transvaal carbonate-banded iron formation platform successions, ascribed largely to globally high sea levels, allied to an aggressive weathering regime. Evidence for both eustasy and weathering are limited in the preserved basin-fill of the Palaeoproterozoic Timeball Hill (upper Transvaal Supergroup, Kaapvaal) depository, formed during the ca. 2.4-2.2 Ga global glaciation, probably due to tectonic subsidence. For the ca. 1.7-1.5 Ga Espinhaco basin (São Francisco craton, Brazil) evidence supports lithospheric stretching and thermal subsidence as prime influences. The origin of greenstone basins remains contentious. That magmatism was a major factor in their evolution is accepted by most, but whether this was plate-independent or plate-driven is less certain; the role of mantle plumes and the possibility of greenstones having been ridge-generated are also discussed by some workers. Episodic magmatism on a global scale may have played a role in the evolution of early basins such as the greenstones, Witwatersrand and Ventersdorp, and with a possible transition to plate tectonics into the Palaeoproterozoic, mid-ocean ridge growth related to either supercontinent break-up or to continental crustal growth rates probably influenced the eustatically controlled Hamersley and Lower Transvaal basin sedimentation. The possibility that early plate tectonics was characterised by variable spreading and subduction rates is discussed in the light of evidence from the Witwatersrand basin, the North American, Baltic and Siberian cratons, and the Transvaal Supergroup. In conclusion, Precambrian basin evolution probably reflects the variable interaction of tectonism, magmatism, eustasy and palaeoclimate (as also found for Phanerozoic basins), with the most significant difference compared to younger basins lying in the relative rates of processes such as ridge-spreading, subduction, crustal growth, weathering and atmospheric compositional change.},
keywords = {},
pubstate = {published},
tppubtype = {article}
}

Precambrian and younger basins reflect the interaction of sediment supply and subsidence; the latter is generally ascribed to tectonic, magmatic and related thermal processes. The interplay of supply and subsidence is further modified by eustasy and palaeoclimate. Problems and enigmas inherent in analysis of Precambrian basin-fills include: a spectrum of ideas on the maximum age of Phanerozoic-style plate tectonics in the rock record; Archaean heat flow up to two to three times present values; changes in magmatism over time (including global magmatic events); the evolution of atmospheric composition and of life and their influence on weathering, erosion and sediment supply rates; degree of preservation, deformation and metamorphism, and preservational bias (especially of intracratonic basins which would lack evidence for early plate tectonics); a limited rock record; poor age constraints, inherent errors in geochronological techniques and difficulty in dating the time of deposition of sedimentary rocks. Major influences on Precambrian basin formation are assumed to include magmatism, plate tectonics, eustasy and palaeoclimate, all of which interacted. Models for greenstone belt evolution include plate tectonic intra-oceanic generation, plume-generated oceanic plateau, and global catastrophic magmatic events that may have been transitional to a plate tectonic regime over several hundred million years. The latter transition may have included the onset of the supercontinent cycle. Insignificant preservation of Precambrian ocean floor makes evaluation of these models problematic. Eustasy was intrinsically related to continental crustal growth rates, continental freeboard and the hypsometric curves of emerging cratons. Possible maximum crustal growth rates near the Archaean-Proterozoic boundary led to globally elevated sea levels, and the formation of enormous carbonate-banded iron formation platforms where cyanobacterial mats, which produced oxygen, flourished. The combination of changes in cratonic growth rates, thermal elevation of cratons, eustasy, weathering and palaeo-atmosphere composition may have combined to produce the first global glaciation at ca. 2.4-2.2 Ga. Examples of basins discussed here emphasise the interaction of tectonism, magmatism, eustasy and palaeoclimate in their evolution. For the Neoarchaean Witwatersrand basin (Kaapvaal craton, South Africa), evidence for all these factors is preserved in the basin-fill, whereas for the Neoproterozoic Macaúbas basin (São Francisco craton, Brazil), clear evidence for eustasy is more limited. The ca. <2.45-<1.9 Ga preserved Hurwitz basin (Hearne domain, Canada) suggests a predominant tectonic control, but with significant influences from magmatic processes, eustasy and palaeoclimate. For the ca. 2.7 Ga Ventersdorp Supergroup, which succeeded the Witwatersrand Supergroup, a strong case can be made for magmatism as a prime influence, with an inferred mantle plume having caused lithospheric stretching and thermal subsidence. The Ventersdorp formed part of an inferred global magmatic event, succeeded on the Pilbara and Kaapvaal cratons by the NeoArchaean-Palaeoproterozoic Hamersley and Lower Transvaal carbonate-banded iron formation platform successions, ascribed largely to globally high sea levels, allied to an aggressive weathering regime. Evidence for both eustasy and weathering are limited in the preserved basin-fill of the Palaeoproterozoic Timeball Hill (upper Transvaal Supergroup, Kaapvaal) depository, formed during the ca. 2.4-2.2 Ga global glaciation, probably due to tectonic subsidence. For the ca. 1.7-1.5 Ga Espinhaco basin (São Francisco craton, Brazil) evidence supports lithospheric stretching and thermal subsidence as prime influences. The origin of greenstone basins remains contentious. That magmatism was a major factor in their evolution is accepted by most, but whether this was plate-independent or plate-driven is less certain; the role of mantle plumes and the possibility of greenstones having been ridge-generated are also discussed by some workers. Episodic magmatism on a global scale may have played a role in the evolution of early basins such as the greenstones, Witwatersrand and Ventersdorp, and with a possible transition to plate tectonics into the Palaeoproterozoic, mid-ocean ridge growth related to either supercontinent break-up or to continental crustal growth rates probably influenced the eustatically controlled Hamersley and Lower Transvaal basin sedimentation. The possibility that early plate tectonics was characterised by variable spreading and subduction rates is discussed in the light of evidence from the Witwatersrand basin, the North American, Baltic and Siberian cratons, and the Transvaal Supergroup. In conclusion, Precambrian basin evolution probably reflects the variable interaction of tectonism, magmatism, eustasy and palaeoclimate (as also found for Phanerozoic basins), with the most significant difference compared to younger basins lying in the relative rates of processes such as ridge-spreading, subduction, crustal growth, weathering and atmospheric compositional change.

@article{smithies_development_2001,
title = {Development of the Archaean Mallina Basin, Pilbara Craton, northwestern Australia; a study of detrital and inherited zircon ages.},
author = {R.H. Smithies and D.R. Nelson and G. Pike},
url = {http://www.geochron.com.au/wp-content/uploads/2016/11/98.-Smithies-et-al-2001.pdf},
year = {2001},
date = {2001-01-01},
journal = {Sedimentary Geology},
volume = {141-142},
pages = {79--94},
abstract = {SHRIMP U-Pb zircon dates are combined with an examination of the age distribution patterns and provenance of both detrital zircons and of zircon xenocrysts in granites to investigate the development of the Archaean Mallina Basin, in the granite-greenstone terrain of the Pilbara Craton, northwestern Australia. The oldest dated components of the basin are c. 3010 Ma volcaniclastic rocks in the western part of the area. New data indicate that siliciclastic turbidites that dominate the southern and eastern part of the basin were deposited at or after c. 2970 Ma but before c. 2955 Ma. Linking both the detrital zircon populations as well as zircon xenocrysts from granites that intruded the Mallina Basin to well-dated areas of the Pilbara granite-greenstone terrane indicates that the sediment was derived from the south, north, northwest, and east. The basin probably evolved primarily in an intracontinental setting between two elevated land masses to the southeast and northwest. Most of the rocks within the basin were folded before intrusion of granites, the oldest of which has been dated at 2954 ± 4 Ma. Evidence of a second depositional cycle is provided by a maximum depositional age of 2941 ± 9 Ma, indicated by a detrital zircon population from a sample of wacke from the southeast part of the Mallina Basin. This second depositional phase may have been related to renewed extension, and recycling of sedimentary rocks within the basin.},
keywords = {},
pubstate = {published},
tppubtype = {article}
}

SHRIMP U-Pb zircon dates are combined with an examination of the age distribution patterns and provenance of both detrital zircons and of zircon xenocrysts in granites to investigate the development of the Archaean Mallina Basin, in the granite-greenstone terrain of the Pilbara Craton, northwestern Australia. The oldest dated components of the basin are c. 3010 Ma volcaniclastic rocks in the western part of the area. New data indicate that siliciclastic turbidites that dominate the southern and eastern part of the basin were deposited at or after c. 2970 Ma but before c. 2955 Ma. Linking both the detrital zircon populations as well as zircon xenocrysts from granites that intruded the Mallina Basin to well-dated areas of the Pilbara granite-greenstone terrane indicates that the sediment was derived from the south, north, northwest, and east. The basin probably evolved primarily in an intracontinental setting between two elevated land masses to the southeast and northwest. Most of the rocks within the basin were folded before intrusion of granites, the oldest of which has been dated at 2954 ± 4 Ma. Evidence of a second depositional cycle is provided by a maximum depositional age of 2941 ± 9 Ma, indicated by a detrital zircon population from a sample of wacke from the southeast part of the Mallina Basin. This second depositional phase may have been related to renewed extension, and recycling of sedimentary rocks within the basin.